REDEFINITION OF THE SEDIMENTARY TIME OF THE SALAWUSU FORMATION IN THE HONGSIBU BASIN, NINGXIA AND ITS SIGNIFICANCE
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摘要: 以沉积旋回划分为基础，采用光释光和碳十四测年技术手段，将宁夏红寺堡盆地上更新统地层时代进行了重新划分与厘定。研究结果将红寺堡盆地原定为萨拉乌苏组的湖相沉积解体为上下两套，下部湖相沉积即为传统意义上的萨拉乌苏组，上部湖相沉积结合区域地层对比结果将其重新划归为水洞沟组，总体上反映了晚更新世青藏高原东北缘发育的两期重要的古大湖事件。在深海大洋氧同位素曲线上这两期古大湖事件分别相当于MIS3与MIS5段，代表了区域上两期温暖湿润的气候环境，也与该时期全球古气候环境的变迁基本一致。同时，在这两期古大湖发育期间，存在一期重要的构造隆升事件，表现为两套地层之间存在明显的区域不整合接触，可能是青藏高原晚更新世强烈隆升的响应。因此，针对青藏高原东北缘上更新统萨拉乌苏组湖相沉积层开展系统的年代学研究，对其地层时代进行重新划分与厘定，对于研究晚更新世古大湖形成与演化、古气候变迁以及青藏高原的隆升提供了重要的地质背景资料。Abstract: Based on the detailed field profile observation and stratigraphic correlation works, we re-divide the Late Pleistocene sedimentary cycle in the Hongsibu basin, Ningxia. What's more, we also redefine the sedimentary frame of the Pleistocene in the Hongsibu basin combining with the accurate time limit from the OSL or 14C dating results. The lacustrine deposit of the former Salawusu formation can be subdivided into the lower part which corresponds with the traditional Salawusu formation, and the upper part which corresponds with the Shuidonggou formation according to the regional stratigraphic comparison. Overall, the sedimentary process of these two parts covered two periods in which large paleo-lakes developed at the north-eastern margin of the Tibet Plateau during the Late Pleistocene. Besides that, these two periods in which large paleo-lakes developed corresponded to the marine oxygen isotope stage 3 (MIS 3) and stage 5 (MIS 5). During these two stages, the paleoclimate around the world was warm and wet, which means the evolution of the paleoclimate at the north-eastern margin of the Tibet Plateau took concerted action with the whole world. Moreover, there also exits a regional unconformity between these two sets of lacustrine deposits which means there developed a significant tectonic uplift during the sedimentation of these two large paleo-lakes. The tectonic uplift might have close relationship with the uplift of the Tibet Plateau during the Late Pleistocene. Therefore, the sedimentary time re-definition of the Salawusu formation is of great significance to the study of the formation and evolution of the Pleistocene large paleo-lakes, transition of the paleo-environment, and the tectonic uplift of the Tibet Plateau during the Late Pleistocene.
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Key words:
- Late Pleistocene /
- Salawusu formation /
- Shuidonggou formation /
- large paleo-lake /
- Hongsibu basin
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图 1 宁夏红寺堡盆地及其邻区地质简图
Figure 1. Regional geological map of Hongsibu Baisn and its adjacent areas
图 2 宁夏红寺堡盆地地层接触关系及沉积特征典型照片
Figure 2. Typical photos showing the contact relationship and sedimentary characteristics of the strata in the Hongsibu basin, Ningxia
图 3 HSB-OSL-7光释光信号衰减曲线和校正后的等效剂量生长曲线图
Figure 3. OSL signal De distribution and equivalent dose growth curve of sample HSB-OSL-7
图 4 碳十四样品测年曲线图
Figure 4. Diagrams of 14C dating curves of samples from the Hongsibu basin, Ningxia
图 5 青藏高原东北缘上更新统地层综合对比图
Figure 5. Comprehensive comparison for the Late Pleistocene strata at the north-eastern margin of the Tibet Plateau
图 6 红寺堡盆地晚更新世沉积序列与深海氧同位素曲线对比图
Figure 6. Comparison between the Late Pleistocene stratigraphic sequence in the Hongsibu basin and marine oxygen isotope curve
图 7 萨拉乌苏组与水洞沟组不整合接触典型照片
Figure 7. Typical photos showing the unconformity between the Salawusu formation and the Shuidonggou formation
表 1 宁夏红寺堡盆地光释光年龄及其参数统计表
Table 1. Statistical table of OSL dating results of samples from Hongsibu basin, Ningxia
样品编号 U/×10-6 Th/×10-6 K/% 环境剂量率/(Gy/ka) 测试粒径/μm 测试方法 等效剂量/Gy 年龄/ka HSB-OSL-9 2.26 8.58 1.71 3.59 4~11 SMAR 41.09±2.32 11.45±1.32 HSB-OSL-8 2.26 8.98 1.74 3.66 4~11 SMAR 70.63±4.07 19.29±2.23 HSB-OSL-7 2.04 8.76 1.88 3.70 4~11 SMAR 92.26±10.06 24.92±3.69 HSB-OSL-6 2.47 9.71 1.95 4.02 4~11 SMAR 217.80±13.65 54.12±6.39 HSB-OSL-5 2.3 9.21 1.76 3.72 4~11 SMAR 228.93±20.81 61.56±8.32 HSB-OSL-4 8.15 11.10 1.98 5.94 4~11 SMAR 472.24±33.01 79.48±9.70 HSB-OSL-3 2.94 11.90 2.38 4.70 4~11 SMAR 421.03±24.60 89.62±10.38 HSB-OSL-2 3.49 10.80 2.27 4.71 4~11 SMAR 531.08±54.01 112.64±16.07 HSB-OSL-1 2.78 7.31 1.82 3.85 4~11 SMAR 458.08±35.46 119.04±15.05 
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